Clay mineral sedimentation in high northern latitude deep-sea basins since the Middle Miocene (ODP Leg 151, NAAG)

Winkler, Amelie; Wolf-Welling, T. C. W.; Stattegger, Karl; Thiede, Jörn

doi:10.1007/s005310100199

Cited by 77 publications

(79 citation statements)

References 52 publications

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“…This Early Messinian reversed precipitation gradient is of special interest, because it occurs during two periods of sea-level lowering in the Eastern Paratethys; the late Maeotian (N6 Ma) and the Portaferrian (5.8 to 5.5 Ma; Krijgsman et al 2010). The low absolute rainfall values in the Paratethys area may indicate that potential evapotranspiration significantly exceeded the precipitation, which supports the hypothesis of a negative hydrologic balance in the Paratethys during the Early Messinian by Krijgsman et al, 2010. The decreasing tendency of the gradient towards the end of the Miocene may be ascribed to further global cooling, especially on the Northern Hemisphere, with more widespread continental ice-sheets, as indicated by ice-rafted debris in the Fram Strait (Winkler et al, 2002) and Irminger Basin (St. John and Krissek, 2002) and by increasing δO 18 in the North Atlantic (Hodell et al, 2001). These observations suggest a more pronounced latitudinal temperature gradient on the Northern Hemisphere, so that the gradient in precipitation may reflect a response to the temperature gradient.…”

Section: Discussionsupporting

confidence: 58%

Miocene precipitation in Europe: Temporal trends and spatial gradients

Böhme

Winklhofer²,

Ilg

2011

Palaeogeography, Palaeoclimatology, Palaeoecology

133

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It is known from present-day climates that both temporal and spatial variations in precipitation can be more pronounced than those in temperature and thus influence ecosystems and human society in more substantial way. However, very little is known about such variations in the past. Here we present an analysis of 206 palaeoprecipitation data from two twelve million year long proxy records of precipitation for Southwest (Calatayud-Teruel basin) and Central Europe (Western and Central Paratethys), spanning the late Early and Middle to Late Miocene (17.8-5.3 Ma) at a temporal resolution of about 80 kyr and 200 kyr, respectively. The estimates of precipitation are based on the ecophysiological structure of herpetological assemblages. The results show that precipitation variations in both regions have large amplitudes during the Miocene with comparable temporal trends at longer time scales. With locally 300 mm up to more than 1000 mm more rainfall per year than present, the early Langhian and the Tortonian were relatively wet periods, whereas the late Langhian and late Serravallian were relatively dry, with up to 300 to 500 mm less precipitation than present. The most humid time intervals were the early and middle Tortonian washhouse climate periods. Overall, our data suggest that the latitudinal precipitation gradient in Europe from the Middle to Late Miocene were highly variable, with a general tendency towards a reduced gradient relative to present day values. The gradient decreases during cooling periods and increases during warming periods, similar to results from simulations of future climate change. Interestingly, the precipitation gradient was reversed during the second washhouse climate period and the Early Messinian, which may have causes a negative hydrologic balance in the Eastern Paratethys during the latter time. Yet, our reconstructed gradient curve shows no direct correlation with the global temperature signal from oxygen isotopes, which implies a non-linear regional response. Our results further suggest that major fluctuations in the precipitation gradient can be responsible for shifts in ecosystem distribution, and particularly, for faunal turnover in South Western Europe.

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Section: Discussionsupporting

confidence: 58%

Miocene precipitation in Europe: Temporal trends and spatial gradients

Böhme

Winklhofer²,

Ilg

2011

Palaeogeography, Palaeoclimatology, Palaeoecology

133

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“…Although it has been speculated that a Neogene Greenland Ice Sheet has existed since at least 18 Ma (Thiede et al, 2011), published records suggest that small scale glaciations large enough to reach sea-level might have occurred on Greenland not before the early to middle Late Miocene (Schaeffer and Spiegler, 1986;Wolf and Thiede, 1991;Fronval and Jansen, 1996;Wolf-Welling et al, 1996;Helland and Holmes, 1997;Winkler et al, 2002). In contrast, ice sheets probably developed in the northern Barents Sea and on Scandinavia already in the Middle Miocene (Fronval and Jansen, 1996;Knies and Gaina, 2008).…”

Section: Introductionmentioning

confidence: 99%

“…4; Shipboard Scientific Party, 1995) prove ice rafting since that time, and suggest a link between observed assemblage changes and the Mi-6 event. Increased bulk accumulation rates at ODP Site 909 supposedly reflect intensification of water mass exchange through Fram Strait (Wolf-Welling et al, 1996;Winkler et al, 2002), which would have resulted in enhanced advection of comparatively cold, low saline, and presumably ice covered waters into the Iceland Sea, forcing the observed changes in the palynomorph assemblage. The increased advection of colder waters may have triggered the coeval collapse in accumulation of Chaetoceros resting spores reflecting a diminished diatom production (Stabell and Koç, 1996).…”

Section: Glacial Inception In the Iceland Sea (~107-102 Ma)mentioning

confidence: 99%

“…The increased advection of colder waters may have triggered the coeval collapse in accumulation of Chaetoceros resting spores reflecting a diminished diatom production (Stabell and Koç, 1996). Benthic δ 18 O values on Vøring Plateau indicate substantial deep water cooling at~11 Ma (Fronval and Jansen, 1996), and increased circum-Arctic IRD fluxes between 11.0 and 9.5 Ma (Schaeffer and Spiegler, 1986;Thiébault et al, 1989;Wolf and Thiede, 1991;Fronval and Jansen, 1996;Wolf-Welling et al, 1996;Helland and Holmes, 1997;Winkler et al, 2002) prove general cooling in the high northern latitudes. The timing of IRD events broadly corresponds to a major uplift phase on Greenland (Thomson et al, 1999;Japsen et al, 2006) suggesting a pivotal role in establishing the Greenland Ice Sheet during Late Miocene times, when pCO 2 stabilized at pre-industrial values (Pagani et al, 1999).…”

Section: Glacial Inception In the Iceland Sea (~107-102 Ma)mentioning

confidence: 99%

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Response of marine palynomorphs to Neogene climate cooling in the Iceland Sea (ODP Hole 907A)

Schreck

Méheust

Stein

et al. 2013

Marine Micropaleontology

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The present study on ODP Leg 151 Hole 907A combines a detailed analysis of marine palynomorphs (dinoflagellate cysts, prasinophytes, and acritarchs) and a low-resolution alkenone-based sea-surface temperature (SST) record for the interval between 14.5 and 2.5 Ma, and allows to investigate the relationship between palynomorph assemblages and the paleoenvironmental evolution of the Iceland Sea. A high marine productivity is indicated in the Middle Miocene, and palynomorphs and SSTs both mirror the subsequent long-term Neogene climate deterioration. The diverse Middle Miocene palynomorph assemblages clearly diminish towards the impoverished assemblages of the Late Pliocene; parallel with a somewhat gradual decrease of SSTs being as high as 20°C at~13.5 Ma to around 8°C at~3 Ma. Superimposed, palynomorph assemblages not only reflect Middle to Late Miocene climate variability partly coinciding with the short-lived global Miocene isotope events (Mi-events), but also the initiation of a proto-thermohaline circulation across the Middle Miocene Climate Transition, which led to increased meridionality in the Nordic Seas. Last occurrences of species cluster during three events in the Late Miocene to Early Pliocene and are ascribed to the progressive strengthening and freshening of the proto-East Greenland Current towards modern conditions. A significant high latitude cooling between 6.5 and 6 Ma is depicted by the supraregional "Decahedrella event" coeval with lowest Miocene productivity and a SST decline. In the Early Pliocene, a transient warming is accompanied by surface water stratification and increased productivity that likely reflects a high latitude response to the global biogenic bloom. The succeeding crash in palynomorph accumulation, and a subsequent interval virtually barren of marine palynomorphs may be attributed to enhanced bottom water oxygenation and substantial sea ice cover, and indicates that conditions seriously affecting marine productivity in the Iceland Sea were already established well before the marked expansion of the Greenland Ice Sheet at 3.3 Ma.

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“…Unfortunately, only few details of the exact extent of sea ice are known for this period. A local glaciation at Svalbard is thought to have yielded a general strengthening of NHG at $ 6.9 Ma (Winkler et al, 2002) and an enhanced sea-ice extent at the Greenland Sea between $ 7.5 and 6.2 Ma (Wolf-Welling et al, 1996). The enhanced sea-ice extent would easily have resulted in a shift of the NCW formation area south towards the Norwegian Sea (Fig.…”

Section: Unit Suiii (75-45 Ma)mentioning

confidence: 99%